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The Pre-Elsterian Valley System in the Western Sudetes, Southwestern Poland, and Its Later Transformation

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The Pre-Elsterian Valley System in the Western Sudetes, Southwestern Poland, and Its Later Transformation Geologia Sudetica, 1998, 31:317-328. The pre-Elsterian valley system in the Western Sudetes, southwestern Poland, and its later transformation Marek Michniewicz Panstwowy Instytut Geologiczny, Oddziai Dolnoslqski, Jaworowa 19, 53-122 Wrodaw, Poland Key words: buried valleys, fluvial pattern, glacial deposits, Elsterian glaciation Abstract This paper presents a reconstruction of the pre-Elsterian fluvial pattern in the Western Sudetes Mts using borehole and geophysical data. These valleys were blocked by the advancing Elsterian ice sheet, enabling the proglacial lakes to be formed, and most of them were later covered by the ice sheet which entered into the mountain interior. The valleys are now filled with 5-15 m of 'pre-glaciaP fluvial gravels and a generally thick glacial series. The latter comprises a till and glaciofluvial and glaciolacustrine sediments, including varved clay. The former valleys occur along the axes of the present-day valleys or at their margins, or occur in watershed areas which have been recently abandoned. Post-Elsterian changes in valley pattern is due to the filling of old valleys and epigenetic incision of new valleys along the tributary valleys. The valley fragments which preserved their former position were deeply incised, with the almost complete removal of older deposits. Some fault activity has been documented for that time in the marginal zone of the Sudetes Mts. The Saalian ice sheet only entered the marginal part of the Sudetes Mts, and hydrographic changes from that time are smaller. Manuscript received 15 April 1998, accepted 30 October 1998. INTRODUCTION The analysis of borehole and geophysical prospecting filling of the buried valleys. There are several views on the data indicated that buried valleys in the Western Sudetes age and the number of Scandinavian glaciations in the Su- (Fig. 1) contain sediments from only one glaciation, in- detes Mts.; the most important are: cluding one till, glaciolacustrine clay, silt and fine sand, 1. The Sudetes Mts were glaciated once during the El- which is usually underlain by fluvial gravel and coarse- sterian stage (Genieser, 1936; Schwarzbach, 1942; Dyjor, grained sand. Only at the mountain margin, in the north- 1991) ernmost part of the studied region, are there more till beds 2. The Sudetes Mts were glaciated once during the which suggest more than once ice sheet advance (Mich- early Saalian stage (Wilczynski, 1991) niewicz et al., 1995, 1996). A similar situation has been 3. The Sudetes Mts were glaciated twice and the ex- described in the adjacent part of Germany (Eissmann, tents of ice sheets during both advances were more or less 1975, 1994), where fluvial deposits at the base of buried the same, although the field data are very ambiguous valleys are interpreted as representing the Cromerian- (Jahn, 1960; Jahn & Szczepankiewicz, 1969) early Elsterian stage. Besides the buried valleys, there are 4. The Sudetes Mts were glaciated twice, but the ice some very deep troughs in the marginal part of the moun- sheets from different stages indicated various extents (Ma- tainous region, which may be interpreted as glacial tunnel coun & Kralik, 1995; Badura & Przybylski, 1998; Krzysz- valleys. Similar deep troughs are interpreted in Germany kowski & Stachura, 1998; Krzyszkowski & Biernat, 1998; as having formed during the Elsterian ice sheet advance Krzyszkowski et al., 1998). (KupetzeJrf/., 1989). This problem has not yet been solved satisfactorily The age of the buried valleys and their sediments in (fahn, 1995; Badura & Przybylski, 1998). It seems that the the western Sudetes has not been precisely established, glacial sediments of the interior of the western Sudetes rep- mainly due to the complete lack of organic deposits or resent the Elsterian stage. This interpretation takes into palaeontological findings. The crucial fact is, that all the account the great similarit-y of the studied sequences to valleys are covered by one till, and thus the age of the till those of southeast Germany, and the fact that the ice sheet gives the upper age boundary for the formation and the from the Elsterian glaciation indicated a more southern 318 M. MICHNIEWICZ Fig. 1. The valley pattern of the western Sudetes and its foreland: 1 - pre-Elsterian valleys: a - main valleys, b - tributary valleys; 2 - pre-Elsterian valleys incised deeply during the Middle and Late Pleistocene: a - main valleys, b - tributary valleys; 3 - glacial tunnel valleys; 4 - faults zone of the margin of the Sudetes Mts; 5 - maximum extent of the Saalian glaciation: a - in Germany (after Kupetz etal, 1989), b - in western Sudetes (after Michniewicz etal., 1995,1996); 6- post-Elsterian (a) and post-Saalian (b) hydrographic changes in western Sudetes; 7 - anayled geological and geophysical cross sections, numbers indicate sections discussed in the paper; 8 - sheets of the 1:200,000 geological map: sheets Jelenia Gora (A), Bogatynia (B), Gubin (C), Zielona Gora (D), Leszno (E) and Walbrzych (F). extent than the Saalian ice sheet in the wide region from Distribution and stratigraphy of the buried valleys in Leipzig to the Polish/German border (Eissmann, 1975, the Western Sudetes were recently presented in detail by 1994; Kupetz et al., 1989; Macoun & Kralik, 1995). The Michniewicz et al. (1995, 1996) and Michniewicz (1997). glacial sediments of the Saalian stage probably occur only This paper only presents the general results of this study at the margin of the Western Sudetes (Fig. 1). Thus the and its main aim is to reconstruct the fluvial pattern in the fluvial deposits under discussion are most probably of pre- Western Sudetes before the first Scandinavian glaciation in Elsterian age, and may roughly correlate with the Crome- this region (Fig. 1, 2). The results presented are based on rian-early Elsterian fluvial series of Eissmann (1975, 1994). the analysis of geophysical prospecting and 2649 boreholes However, some other authors, on the basis of data from which were done over the last few decades (Michniewicz et adjacent regions such as the northern part of the Czech al., 1995), as well as of the analysis of new geoelectrical Republic (Macoun & Kralik, 1995) or the Middle Sudetes profiles, which were performed during this project (Mzyk, (Krzyszkowski & Stachura, 1998; Krzyszkowski & Bier- 1995). There are 1234 measuring points along the new geo- nat, 1998) suggest that the early Saalian ice sheet had a electrical profiles, each located from 50 to 200 m apart. much wider extent. The profiles lie perpendicularly to the valleys, and have THE PRE-ELSTERIAN VALLEY SYSTEM IN THE WESTERN SUDETES 319 AB line spacing from 250 m at the margins to up to 1000 penetration down to 50-150 m. m in the axes of the valleys. These parameters gave depth A RECONSTRUCTION OF THE PRE-ELSTERIAN VALLEY SYSTEM THE PRE-BOBR VALLEY SYSTEM prospecting beyond the present-day valley between Papro- tek and Stara Bialka (Fig. 1) documented only bedrock, The upper course of the present-day Bobr river valley indicating a very stable position for the Bobr valley in this is located along the pre-Bobr valley system. In the south- region. In contrast, north of Kamienna Gora, the present- ernmost, non-glaciated region, the young fluvial deposits day and buried valleys have quite different locations. The are superimposed on the older fluvial gravels, forming a 15 former runs west, whereas the latter is present between m thick sequence near Bukowka (Fig. 3). More to the Ciechanowice and Kaczorow (Fig. 1). The buried valley north, near Janiszow, these young and old fluvial se- near Ciechanowice is filled with 10-15 m of fluvial gravels quences are separated by glaciolacustrine clay and silt (Fig. 4). The latter was deposited in the proglacial lake formed at the front of the Scandinavian ice sheet. Geophysical Fig. 3. Geological cross section (no. 2) through the Bobr valley near Bukowka. Location in Fig. 1.7- location of the boreholes, 2 - the base of Quaternary deposits, 3 - location of the geophysi- cal measuring points, 4 - faults, 5 - lithological boundaries, 6 - lithostratigraphic boundaries. Lithology: 7 - brown coal, 8 - varved clay, 9 - varved silt, 10 - silt, 11 - sandy silt, 12 - fine- grained sand and silt, 13 - fine-grained sand, 14 - medium- and coarse-grained sand, 15 - mixed, fine- to coarse-grained sand, 16 - Fig. 2. Longitudinal profiles along the buried valleys of the west- pebble sand, 17 - pebble gravel, 18 - cobble gravel, 19 - till or ern Sudetes: pre-Bobr (A), pre-Prusicki Potok (C), pre-Kamienna glaciolacustrine diamictons, 20 - slope deposits, mainly diamic- and pre-Lomnica, pre-Kwisa (D) and pre-Nysa and pre-Witka (E). tons, 21 - artificial deposits. Stratigraphy: Q - Quaternary, H - / - the bottom surface of the valley axes, 2 - valley fragments Holocene, B - Weichselian, W - late Saalian (Wartanian), O - glacially incised during the Elsterian glaciation, 3 - the base of early Saalian (Odranian), M - Holsteinian, E - Elsterian; Li- Quaternary deposits in tunnel valleys, 4 - valley fragments in- thological indexes on cross sections: d - fine-grained colluvium, r cised during the post-Elsterian time, 5 - position of the base of - coarse-grained colluvium, 1 - loess, li - lacustrine deposits, b - Quaternary deposits in boreholes, 6 - interpreted position of the glaciolacustrine deposits (bd - lower, bg - upper), fg - glaciofluvial base of Quaternary deposits in geophysical profiles, 7 - other deposits (fga - lower, fgg - upper), g - glacial deposits (till), f - boreholes. fluvial deposits. 320 M. MICHNIEWICZ Fig. 4. Geological cross section (no 3) through the pre-Bobr val- ley near Janiszow. Location in Fig. 1, explanations in Fig. 3. Fig. 5. Geological cross section (no 4) through the pre-Bobr val- ley near Ciechanowice. Location in Fig. 1, explanations in Fig. 3. Fig. 7. Interpretation of the geological structure (section no 6) of the pre-Bobr valley near Wojcieszow based on geophysical data. Location in Fig. i, explanations in Fig. 3. Kaczawa valley, with the probable exception of a short fragment near Swierzawa, and then turns west, to the pre- sent-day Skora valley (Fig.
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